GEOL483.3 GEOL882.3 Elements of Rock...
Transcript of GEOL483.3 GEOL882.3 Elements of Rock...
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Elements of Rock Mechanics
Stress and strain
Creep
Constitutive equationHooke's law
Empirical relations
Effects of porosity and fluids
Anelasticity and viscoelasticity
Reading:➢ Shearer, 3
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Stress
Consider the interior of a deformed body: At point P, force dF acts on
any infinitesimal area dS. dF is a projection of stress tensor, s, onto n:
Stress sij is measured in [Newton/m2], or Pascal
(unit of pressure).
dF can be decomposed into two components relative to the orientation of the surface, n:
Parallel (normal stress)
Tangential (shear stress, traction)
dF i= ij n j dS
dF ni=ni⋅(projection of F onto n)=ni kj nk n j dS
Note summation over k and jdF =
dF− dFn
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Forces acting on a small cube
Consider a small parallelepiped (dx dydz=dV) within the elastic body.
Exercise 1: show that the force applied to the parallelepiped from the outside is:
(This is simply minus divergence (“convergence”) of stress!)
Exercise 2: Show that torque applied to the cube from the outside is:
F i=−∂ j ij dV
Li=−ijk jk dV
Keep in mindimplied summations over repeated indices
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Symmetry of stress tensor
Thus, L is proportional to dV: L = O(dV)
The moment of inertia for any of the axes is proportional to dVlength2:
and so it tends to 0 faster than dV: I = o(dV).
Angular acceleration: q = L/I, must be finite as dV 0, and therefore:
Consequently, the stress tensor is symmetric:
ij =
ji
ji has only 6 independent parameters out of 9:
I x=∫dV
y2z2dV
Li /dV=−ijk jk=0.
Big “O”
Little “o”
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Principal stresses
The symmetric stress matrix can always be diagonalized by properly selecting the (X, Y, Z) directions (principal axes)
For these directions, the stress force F is orthogonal to dS (that is, parallel to directional vectors n)
With this choice of coordinate axes, the stress tensor is diagonal:
Negative values mean pressure,
positive - tension
For a given s, principal axes and stresses can be found by solving for eigenvectors of matrix s:
σ e i=λ i e i
Principal stress
Principal direction vector
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Mohr's circle
It is easy to show that in 2D, when the two principal stresses equal s
1 and s
2, the normal
and tangential (shear) stresses on surface oriented at angle q equal:
Mohr (1914) illustrated these formulas with a diagram:
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Mohr's circle (cont.)
Two ways to use:
1) When knowing the principal stresses and angle q, start from points s
1, s
2, and find s
n
and st.
When knowing the stress tensor (sxx, s
xy, and
syy), start from points A and B and find s
1, s
2,
and the direction of principal direction s1 (q).
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Strain
Strain is a measure of deformation, i.e., variation of relative displacement as associated with a particular direction within the body
It is, therefore, also a tensorRepresented by a matrix
Like stress, it is decomposed into normal and shear components
Seismic waves yield strains of 10-10-10-6
So we can rely on infinitesimal strain theory
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Elementary Strain
When a body is deformed, displacements (U) of its points are dependent on (x,y,z), and consist of:
Translation (blue arrows below)
Deformation (red arrows)
Elementary strain is: eij=∂U i
∂ x j
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Stretching and Rotation
Exercise 1: Derive the elementary strain associated with a uniform stretching of the body:
x 'y '=1 0
0 1 xy .
Exercise 2: Derive the elementary strain associated with rotation by a small angle a:
What is characteristic about this strain matrix?
x 'y '= cos sin
−sin cosxy.
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Strain Components
Anti-symmetric combinations of eij yield rotations of the body without changing its shape:
e.g., yields rotation about the 'y' axis.
So, the case of is called pure shear (no rotation).
To characterize deformation, only the symmetric component of the elementary strain is used:
12∂U z
∂ x−∂U x
∂ z
∂U z
∂ x=∂U x
∂ z
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Dilatational Strain (relative volume change during deformation)
Original volume: V=xyz
Deformed volume: V+V=(1+xx)
(1+yy)(1+
zz)xyz
Dilatational strain:
Note that shearing (deviatoric) strain does not change the volume.
=VV=1 xx 1 yy1 zz −1≈ xx yy zz
=ii=∂i U i=∇ U=div U
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Deviatoric Strain (pure shear)
Strain without change of volume:
εij=εij−Δ3δij
Trace (εij)≡εii=0
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Constitutive equation
The “constitutive equation” describes the stress developed in a deformed body:
F = -kx for an ordinary spring (1-D)
~ (in some sense) for a 'linear', 'elastic' 3-D solid. This is what these terms mean:
For a general (anisotropic) medium, there are 36 coefficients of proportionality between six independent
ij and six
ij: ij=ij , kl kl .
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Hooke's Law(isotropic medium)
For isotropic medium, the instantaneous strain/stress relation is described by just 2 constants:
ij = d
ij
ij
dij is the “Kronecker symbol” (unit
tensor) equal 1 for i =j and 0 otherwise;
and are called the Lamé constants.
Question: what are the units for and ?
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Hooke's law (anisotropic)
For an anisotropic medium, there are 36 coefficients of proportionality between six independent
ij and six
ij:
ij=ij , kl kl
This is the instantaneous-response
case only
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Elastic moduli
Although and provide a natural mathematical parametrization for s(e), they are typically intermixed in experiment environments
Their combinations, called “elastic moduli” are typically directly measured.
For example, P-wave speed is sensitive to M = l + 2m , which is called the “P-wave modulus”
Two important pairs of elastic moduli are:
Young's and Poisson's
Bulk and shear
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Young's and Poisson's moduli
Depending on boundary conditions (i.e., experimental setup), different combinations of 'and may be convenient. These combinations are called elastic constants, or moduli:
Young's modulus and Poisson's ratio:• Consider a cylindrical sample uniformly
squeezed along axis X:
Note: The Poisson's ratio is more often denoted s
It measures the ratio of l and m:
=
12
−1
E= xx
xx
= 32
= zz
xx
=
2
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Bulk and Shear Moduli
Bulk modulus, K• Consider a cube subjected to hydrostatic
pressure
The Lame constant complements K in describing the shear rigidity of the medium. Thus, is also called the 'rigidity modulus'
For rocks:• Generally, 10 Gpa < < K < E < 200 Gpa
• 0 < < ½ always; for rocks, 0.05 < < 0.45, for most “hard” rocks, is near 0.25.
For fluids, ½ and =0 (no shear resistance)
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Empirical relations:K,l,m(r,V
P)
From expressions for wave velocities, we can estimate the elastic moduli:
=V S2
=V P2−2V S
2
K=23=V P
2−
43
V S2
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Empirical relations:density(V
P)
Nafe-Drake curve for a wide variety of sedimentary and crystalline rocks (Ludwig, 1970):
[g /cm3]=1.6612V P−0.4721V P
2
0.0671V P3−0.0043V P
4
0.000106 V P5
Gardner's rule for sedimentary rocks and 1.5 < V
P < 6.1 km/s (Gardner et
al., 1984):
[g /cm3]=1.74V P
0.25
For crystalline rocks rocks 5.5 < VP <
7.5 km/s (Christensen and Mooney., 1995):
[g /cm3]=0.5410.3601V P
(See the plot is in the following slide)
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Empirical relations:density(V
P)
From T. Brocher, USGS Open File Report 05-1317, 2005
Nafe-Drake curve
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Empirical relations:V
S(V
P)
“Mudline” for clay-rich sedimentary rocks (Castagna et al., 1985)
V S [km/ s ]=V P−1.36/1.16
“Mafic line” for calcium-rich rocks (dolomites), mafic rocks, and gabbros (Brocher, 2005):
V S [km/ s ]=2.88+ 0.52(V P−5.25)
Extension for higher velocity crustal rocks (1.5 < V
P < 8 km/s;
California, Brocher, 2005):
V S [km/ s ]=0.7858−1.2344V P0.7949V P2
−0.1238V P30.0064 V P
4
(See the plot is in the following slide)
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Empirical relations:V
S(V
P)
From T. Brocher, USGS Open File Report 05-1317, 2005
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Effect of pressure
Differential pressure is the difference of confining and pore pressures (related to pressure within rock matrix)
Differential pressure closes cracks and generally increases the moduli, especially K:
Dry carbonate sample from Weyburn reservoir
Note the hysteresis
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Effects of porosity
Pores in rockReduce average density, rReduce the total elastic energy stored, and thus reduce the K and m
Fractures have similar effects, but these effects are always anisotropic
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Effects of pore fluids
Fluid in rock-matrix pores increases the bulk modulus
Gassmann's model (next page)
It has no effect on shear modulus
Relative to rock-matrix r, density effectively decreases:
where rf is fluid density, and a > 1 is the
“tortuosity” of the pores
In consequence, VP and V
S increase, and
the Poisson's ratio and VP/V
S decrease
f 1−a
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Gassmann's equation(“fluid substitution”)
Relates the elastic moduli of fluid-saturated rock (K
s, m
s) to those of dry
porous rock (Kd, m
d):
where Kf is fluid bulk modulus, and K
0 is the bulk
modulus of the matrix
Note:
Assumptions:Isotropic, homogeneous, elastic, monomineralic medium;
Pore space is well-connected and in pressure equilibrium;
Closed system with no fluid movement across boundaries;
No chemical reactions.
K s=KdK 01−Kd /K 0
2
1−K d /K0− 1−K 0/K f
s=d
K fK dK sK 0
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Creep
When step-function stress s(t) = s
0q(t) is applied to a solid, it
exhibits creep:
t =0
M U
[1t ]
“Creep function”
“Unrelaxed modulus”
Relaxation time
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Viscoelasticity
It is thought that creep-like processes also explain:
Attenuation of seismic waves (0.002 – 100 Hz)
Attenuation of Earth's free oscillations (periods ~1 hour)
Chandler wobble (period ~433 days)
General viscoelastic model: stress depends on the history of strain rate
Constitutive equation for the “standard linear solid” (Zener, 1949):
t =∫−∞t
M t− d
Viscoelastic modulus
σ+ τσ σ=M (ε+ τεε)
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Elastic Energy Density
Mechanical work is required to deform an elastic body; as a result, elastic energy is accumulated in the strain/stress field
When released, this energy gives rise to earthquakes and seismic waves
For a loaded spring (1-D elastic body), E= ½kx2=½Fx
Similarly, for a deformed elastic medium, the elastic energy density is:
Eelastic=12σij εij
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Energy Flux in a Wave
Later, we will see that in a wave, the kinetic energy density equals the elastic energy:
Eelastic=12σij εij=1 ove2ρ u2
12σ ijεij=
12ρ u2
The energy propagates with wave speed V, and so the average energy flux equals:
J=VE=ρV ⟨ u2⟩=
12
Z Av2
and so the total energy density:
E=12σij εij+
12ρ u2
=ρu2
where Z = rV is the impedance, and Av is
the particle-velocity amplitude
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Lagrangian mechanics
Instead of equations of motion, modern (i.e., 18th century!) “analytical mechanics” is described in terms of energy functions of generalized coordinates x and velocities x:
Kinetic: (for example)
Potential:
These are combined in the Lagrangian function:
Equations of motion become:
E k=12
m x2
E p=12
k x2
L x , x =Ek−E p
ddt
∂ L∂ x −
d Ld x
=0
.
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Lagrangian mechanicsof elastic medium
Lagrangian of isotropic elastic field:
This shows the true meanings of Lamé parameters
They correspond to the contributions of two different types of deformation (compression and shear) to the potential energy
L u , u=∫dV [12 u i ui−12 ii2 ij ij]
These are the only two second-order combinations of e
that are scalar and invariant with respect to rotations
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GEOL882.3GEOL483.3
Lagrangian mechanics
Exercise: use the Hooke's law to show that
is indeed equivalent to:
Eelastic=12 ij ij
Eelastic=12 ii
2 ij ij